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Geophysical Journal International Geophysical Journal International Geophys. J. Int. (2015) 201, 528–542 doi: 10.1093/gji/ggv041 GJI Geodynamics and tectonics Fault activity in the epicentral area of the 1580 Dover Strait (Pas-de-Calais) earthquake (northwestern Europe) D. Garc´ıa-Moreno,1,2 K. Verbeeck,1 T. Camelbeeck,1 M. De Batist,2 F. Oggioni,3 O. Zurita Hurtado,2 W. Versteeg,2,4 H. Jomard,5 J. S. Collier,3 S. Gupta,3 A. Trentesaux6 and K. Vanneste1 1Royal Observatory of Belgium, Av. Circulaire 3, 1180 Uccle, Brussels, Belgium. E-mail: [email protected] 2Renard Centre of Marine Geology, Ghent University. Krijgslaan 281 S.8,B-9000 Ghent, Belgium 3Department of Earth Science and Engineering, Imperial College London. Prince Consort Road, London SW72BP,United Kingdom 4Vlaams Instituut voor De Zee. InnovOcean site, Wandelaarkaai 7,B-8400 Oostende, Belgium 5Institut de Radioprotection et de Suretˆ eNucl´ eaire.´ Av. de la Division Leclerc 31, Fontenay-aux-Roses, France 6Universite´ Lille 1,Lab.Geosyst´ emes` UMR 8217 Lille1/CNRS, 59 655 Villeneuve d’Ascq, France Downloaded from Accepted 2015 January 20. Received 2015 January 19; in original form 2014 February 12 SUMMARY http://gji.oxfordjournals.org/ On 1580 April 6 one of the most destructive earthquakes of northwestern Europe took place in the Dover Strait (Pas de Calais). The epicentre of this seismic event, the magnitude of which is estimated to have been about 6.0, has been located in the offshore continuation of the North Artois shear zone, a major Variscan tectonic structure that traverses the Dover Strait. The location of this and two other moderate magnitude historical earthquakes in the Dover Strait suggests that the North Artois shear zone or some of its fault segments may be presently active. In order to investigate the possible fault activity in the epicentral area of at North Dakota State University on May 20, 2015 the AD 1580 earthquake, we have gathered a large set of bathymetric and seismic-reflection data covering the almost-entire width of the Dover Strait. These data have revealed a broad structural zone comprising several subparallel WNW–ESE trending faults and folds, some of them significantly offsetting the Cretaceous bedrock. The geophysical investigation has also shown some indication of possible Quaternary fault activity. However, this activity only appears to have affected the lowermost layers of the sediment infilling Middle Pleistocene palaeobasins. This indicates that, if these faults have been active since Middle Pleistocene, their slip rates must have been very low. Hence, the AD 1580 earthquake appears to be a very infrequent event in the Dover Strait, representing a good example of the moderate magnitude earthquakes that sometimes occur in plate interiors on faults with unknown historical seismicity. Key words: Palaeoseismology; Intraplate processes; Submarine tectonics; Neotectonics; Europe. faults and hence the possible present-day seismic hazard related to 1 INTRODUCTION them. Assessing the seismic hazard associated with plate-interior tectonic This study focuses on the poorly known offshore Sangatte Fault, structures is generally a very difficult task. For instance, the seis- which traverses the marine Dover Strait (Pas de Calais) from micity in these areas is generally too low to be studied by means of Sangatte (northeastern France) to Folkestone (southeastern Eng- classic seismotectonic approaches. In addition, destructive earth- land; Figs 1 and 2). This fault is part of the North Artois shear zone quakes are rare and they usually appear randomly distributed in (Fig. 1) and it is believed to be the probable source of the magnitude space and are sometimes located in places with no known histor- ∼6.0 earthquake that occurred offshore in AD 1580 (Camelbeeck ical seismicity (Zoback & Grollimund 2001; Camelbeeck et al. et al. 2007). Historical information suggests that this earthquake 2007). This apparent randomness of the seismicity might be the produced damage equivalent to MSK intensity VIII in Calais and consequence of recurrence intervals too long to have produced two Dover and about VI in London, and it was felt as far as Koln¨ significant ruptures of the same feature in historical times (Stein & (Germany) to the east and York (England) to the north (Neilson Mazzotti 2007). It is thus necessary to adopt palaeoseismic meth- et al. 1984; Melville et al. 1996; Musson 2004). According to ods in order to understand and characterise the activity of intraplate the empirical relationships of Wells & Coppersmith (1994), the 528 C The Authors 2015. Published by Oxford University Press on behalf of The Royal Astronomical Society. Fault activity in the Dover Strait 529 inferred magnitude of the AD 1580 earthquake would correspond different reactivations of structures inherited from the Variscan to an average fault length of 10 km and to a slip of 0.25–0.30 m. Orogeny (e.g. Chadwick et al. 1993; Van Vliet-Lanoe¨ et al. 1998, However, nothing is presently known about any active fault located 2002a,b;Mansyet al. 2003; Minguely et al. 2010). Since its for- in the Dover Strait. mation, the North Artois shear zone has passed from the original Apart from the AD 1580 earthquake, the Sangatte fault has only compressional setting (Variscan Orogeny) through extension related been associated with two other seismic events of moderate magni- to the opening of the Tethyan and Atlantic ocean basins during tude. These are the MS ∼ 4.0 historical earthquake that occurred Jurassic and Cretaceous times, and again to compression during the in 1776 (Melville et al. 1996) and the Mw 4.0 Folkestone earth- tectonic inversion that started in the early Palaeogene epoch due to quake of 2007 (Ottemoller¨ et al. 2009). The hypocentre of the latter the Alpine Orogeny (Vandycke et al. 1988; Bergerat & Vandycke was instrumentally localized about 5 ± 2 km below Folkestone 1994; Van Vliet-Lanoe¨ et al. 2002a,b, 2004;Mansyet al. 2003; (Ottemoller¨ et al. 2009). Minguely et al. 2010). The presence of major infrastructures and the densely populated From an analysis of gravity data, Everaerts & Mansy (2001) cities within the area of influence of an earthquake similar to the concluded that the major fault segments comprising the North Ar- AD 1580 event make it very important to assess the nature of the tois shear zone have lengths ranging from 15 to 40 km and are Sangatte Fault and its tectonic activity over time. In order to do so, arranged as right-stepping en-echelon fault zones (Fig. 2). Based we have gathered a large set of seismic-reflection and bathymetric on their gravity map, Camelbeeck et al. (2007) distinguished five data from the epicentral area of this earthquake. In this paper, we major faults: that is Marqueffles Fault, Ruitz Fault, Pernes Fault, will present and discuss the interpretation of these geophysical data, Landrethun Fault and Sangatte Fault (see Fig. 2). Not only their ac- Downloaded from which resulted in the first high-resolution bathymetric map of the tivity, but the precise geometry of these faults is still poorly known. Dover Strait and provided a clear visualization of the main tectonic This is especially true for the mostly submarine Sangatte Fault, on structures and their activity over time. which there has been no specific study published until now; despite the fact that it corresponds to the most likely geological structure capable of having generated the AD 1580 event (e.g. Camelbeeck http://gji.oxfordjournals.org/ 2 TECTONIC AND GEOLOGICAL et al. 2007). SETTINGS The Quaternary activity of the North Artois shear zone is still The North Artois shear zone is a complex fault-and-fold system debated, as no conclusive field evidence of recent tectonic deforma- defining the western part of the Variscan Midi–Eifel Thrust Front tion has yet been associated with any of its fault segments. Indirect (Fig. 1), which separates the Ardenne Massif and Paris Basin to the evidence includes possible extensional faults identified in the San- south (hanging wall) from the London–Brabant Massif to the north gatte cliff (Van Vliet-Lanoe¨ et al. 2000) and minor right-lateral (footwall). The present-day geometry of this fault zone results from deformations affecting river development and Quaternary fluvial several phases of post-Palaeozoic deformation that have induced and aeolian deposits in northeastern France (Colbeaux et al. 1981; at North Dakota State University on May 20, 2015 Figure 1. Onshore geological map of northwestern Europe updated with the geology of the English Channel and major tectonic structures (De Bethune´ & Bouckaert 1968). Known historical and instrumental earthquakes (Mw ≥ 3) are indicated scaled by magnitude according to catalogues from the Royal Observatory of Belgium and Grunthal¨ et al. (2009). 530 D. Garc´ıa-Moreno et al. Downloaded from http://gji.oxfordjournals.org/ Figure 2. Interpreted horizontal derivative of the Bouguer gravity anomaly (see Everaerts & Mansy 2001; Camelbeeck et al. 2007). The Bouguer anomaly was calculated using the gravity database of the Royal Observatory of Belgium. For France and United Kingdom the data were provided by the French and British Geological Surveys respectively. All gravity data are referenced to the gravity datum Uccle (1976) (IGSN71–0.048mGal). The density reduction used for the at North Dakota State University on May 20, 2015 calculation of the Bouguer anomaly on land was 2.67. Above the sea, the free-air anomaly was used. Grey coloured circle: epicentre of the 2007 Folkestone earthquake (Ottemoller¨ et al. 2009); dashed ellipsoid: isoseismal indicating MSK Intensity VII–VIII during the 1580 earthquake (Melville et al. 1996); LF, Landrethun Fault; SF, Sangatte fault; RF, Ruitz fault; PF, Pernes fault and MF, Marqueffles fault. Van Vliet-Lanoe¨ et al. 2002a;Mansyet al. 2003). The latter suggest long due to the dynamic conditions this area has been subjected to right-lateral strike-slip deformation, which is in good agreement during the Holocene, with strong sediment reworking, erosion and with the NNW–SSE orientation of the maximum horizontal stress sediment starvation (e.g.
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